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USGS Open-File Report 2007-1047, Short Research Paper 047, 4 P.; Doi:10.3133/Of2007-1047.Srp047

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USGS Open-File Report 2007-1047, Short Research Paper 047, 4 P.; Doi:10.3133/Of2007-1047.Srp047 U.S. Geological Survey and The National Academies; USGS OF-2007-1047, Short Research Paper 047; doi:10.3133/of2007-1047.srp047 Geophysical survey reveals tectonic structures in the Amundsen Sea embayment, West Antarctica K. Gohl,1 D. Teterin,2 G. Eagles,1 G. Netzeband,3 J. W. G. Grobys,1 N. Parsiegla,1 P. Schlüter,1 1 1 2 V. Leinweber, R. D. Larter,r G. Uenzelmann-Neben, and G. B. Udintsev 1Alfred Wegener Institute for Polar and Marine Research, Postbox 120161, 27515 Bremerhaven, Germany ([email protected]) 2Vernadsky Institute of Geochemistry and Analytical Chemistry, Laboratory of Geomorphology and Tectonics of the Ocean Floor, 19 Kosygin St., 117975 Moscow, Russia ([email protected]) 3Institute for Geophysics, University of Hamburg, Bundesstr. 55, 20146 Hamburg, Germany (now at: [email protected]) 5British Antarctic Survey, High Cross, Madingley Road, Cambridge, CB3 0ET, UK ([email protected]) Abstract The Amundsen Sea embayment of West Antarctica is in a prominent location for a series of tectonic and magmatic events from Paleozoic to Cenozoic times. Seismic, magnetic and gravity data from the embayment and Pine Island Bay (PIB) reveal the crustal thickness and some tectonic features. The Moho is 24-22 km deep on the shelf. NE- SW trending magnetic and gravity anomalies and the thin crust indicate a former rift zone that was active during or in the run-up to breakup between Chatham Rise and West Antarctica before or at 90 Ma. NW-SE trending gravity and magnetic anomalies, following a prolongation of Peacock Sound, indicate the extensional southern boundary to the Bellingshausen Plate which was active between 79 and 61 Ma. Citation: Gohl, K., D. Teterin, G. Eagles, G. Netzeband, J. W. G. Grobys, N. Parsiegla, P. Schlüter, V. Leinweber, R. D. Larter, G. Uenzelmann- Neben, and G. B. Udintsev (2007), Geophysical survey reveals tectonic structures in the Amundsen Sea embayment, West Antarctica, in Antarctica: A Keystone in a Changing World – Online Proceedings of the 10th ISAES, edited by A. K. Cooper and C. R. Raymond et al., USGS Open-File Report 2007-1047, Short Research Paper 047, 4 p.; doi:10.3133/of2007-1047.srp047 Introduction The newest geophysical data from the Amundsen Sea The Amundsen Sea embayment with its eastern sector, Embayment and PIB (Figure 1) reveal crustal thickness Pine Island Bay (PIB) (Figure 1), is in a tectonically and tectonic features and lineations. These early results prominent position suggested to be the location of a are discussed in context with plate-kinematic crustal boundary between the Marie Byrd Land block to reconstructions of the early stages of continental breakup the west and the Thurston Island/Ellsworth Land blocks to and southern Pacific seafloor spreading. the east which was active during the Mesozoic break-up of Gondwana or even before (e.g. Dalziel and Elliot, 1982; Storey, 1991; Grunow et al., 1991). Eagles et al. (2004) illustrate that early Pacific-Antarctic separation evolved first as rifting and crustal extension along the present-day Bounty Trough between Chatham Rise and Campbell Plateau (Grobys et al., 2007). It possibly continued along the present Great South Basin between the Campbell Plateau and the South Island of New Zealand at 90 Ma until the rift was abandoned in favour of a new extensional locus to the south, forming the earliest oceanic crust between Campbell Plateau and Marie Byrd Land at 84-83 Ma. The boundary between Chatham Rise and Campbell Plateau – with Bounty Trough closed before 90 Ma – is situated off the western Figure 1. Overview map of the Amundsen Sea Amundsen Sea Embayment at about 120°-125° W. embayment and Pine Island Bay showing the satellite- derived gravity anomaly grid of McAdoo and Laxon The Bellingshausen Plate (Stock and Molnar, 1987) (1997) and the locations of two deep crustal seismic moved independently on the southern flank of the mid- (dashed red lines) and multi-channel seismic profiles (red Pacific spreading ridge from Late Cretaceous times until lines) collected during RV Polarstern expedition ANT- about 61 Ma when a major plate reorganisation occurred XXIII/4. The dotted bold black lines mark the in the South Pacific (e.g. Larter et al., 2002; Eagles et al., approximate location of the interpreted incipient narrow 2004). The small plate’s western boundary was situated in rift basin. Its trend is aligned with a gravity anomaly north the area of the Marie Byrd Seamounts (Heinemann et al., of Thurston Island. The dashed black lines illustrate the 1999), its eastern transpressional boundary along a gravity presumed location of the southern Bellingshausen Plate anomaly lineament in the western Bellingshausen Sea. boundary. The box marks the area of the Moho depth map The southern boundary may have been active along the of Figure 4. PT Pine Island Through, PGA Peacock WNW-ESE striking Peacock Gravity Anomaly (PGA) Gravity Anomaly, PS Peacock Sound, PG Pine Island across the outer continental shelf of the Amundsen Sea Glacier, TG Thwaites Glacier. embayment (Larter et al., 2002; Eagles et al., 2004). 10th International Symposium on Antarctic Earth Sciences Geophysical data acquisition in the Amundsen reveals a NE-SW trending system of near-parallel positive Sea Embayment magnetic anomaly lineations as the dominant feature in The Alfred Wegener Institute and British Antarctic the western embayment (Figure 2). The lineations run Survey cooperated closely during early 2006 with RV parallel to the trend of the satellite-derived gravity Polarstern’s expedition ANT-XXIII/4 and RRS James C. anomalies across the middle shelf and that of sharp Ross’ cruise JR141. Extensive geophysical datasets were positive linear gravity anomaly north of Thurston Island. collected as part of a research program dedicated to the The magnetic grid over the eastern PIB reveals scattered study of tectonic, sedimentary and glacial advance/retreat patches of positive and negative anomalies with no processes in the Amundsen Sea Embayment and PIB significant lineations, except for a the short WNW trend (Larter et al., 2007). For this paper, we primarily use the of positive anomalies west of the Peacock Sound. This resulting deep crustal seismic profiles, shipborne gravity anomaly lies on top of, and has the same orientation as, and magnetic data collected from the Polarstern, and an the PGA, but it does not follow the PGA farther extensive aeromagnetic survey of 20,000 km flown by the northwest. However, gravity modeling indicates an Polarstern helicopters (Figures 1 and 2). Due to an area elongated body of high-density, possibly magmatic of inaccessibility, the magnetic data mainly cover two material along the PGA. Some of the scattered magnetic separate areas: the western Amundsen Sea embayment anomalies in the south may be attributed to the numerous and the southern and eastern PIB region. The analysis of igneous and meta-igneous bodies observed in outcrops on these data was complemented by the few previously- islands in PIB and along its eastern mainland shore as existing seismic and potential field data from the shelf observed by the SPRITE Group (1992) and on our break to the oceanic parts of the Amundsen Sea (Gohl et Polarstern cruise. al., 1997; Nitsche et al., 2000) and by the satellite-derived gravity anomaly field of McAdoo & Laxon (1997). We acquired deep crustal seismic wide-angle reflection and refraction data with one profile across the inner to middle continental shelf of the western embayment (AWI-20060100) and another running from the foot of the slope towards the Marie Byrd Seamount cluster of the continental rise (AWI-20060200) (Figure 1). Shots from an airgun cluster, consisting of 8 G.Guns™ with a total volume of 68 liters (4160 in3), fired with 190 bar at a 1-minute interval (150 m nominal spacing), resulted in good quality data with identified phases from the upper to lower crust and the uppermost mantle on both profiles. Restricted by massive pack-ice to the north, west and east and by drifting sea-ice patches, only nine ocean- bottom hydrophone (OBH) systems could be deployed at 18-19 km spacing on the shelf, in order to minimize the risk of instrument loss. Seven OBH systems with the same nominal spacing were deployed along the deep-sea Figure 2. Map of gridded magnetic anomalies in the profile. About 2200 km of multi-channel seismic (MCS) Amundsen Sea embayment from helicopter-magnetic profiles were acquired in the Amundsen Sea Embayment surveying and ship-board magnetic data of ANT-XXIII/4. and in PIB using a 600-m long analogue streamer. We Dashed black lines indicate linear anomaly trends. Thin also recorded low-fold normal-incidence reflection data dark blue lines denote seismic reflection profiles of ANT- from the airgun shots along both OBH profiles with the XXIII/4. Thick dark blue lines mark the locations of deep same streamer. 530 km of single-channel seismic data crustal seismic profiles (the southern profile AWI- were recorded in the embayment during the JR141 cruise 20060100 corresponds to model in Figure 3). (Larter et al., 2007). For this study, we use parts of the MCS dataset to identify the depth of the acoustic The P-wave phases recorded by eight OBH systems of basement to constrain thickness and geometries of the shelf profile AWI-20060100 were modeled for a crustal sediment cover in the seismic refraction and gravity velocity-depth structure using a raytracing and travel-time modelling process. Details of the seismic reflection data inversion method. The final velocity-depth model with regard to glacial-marine sedimentation processes will (Figure 3) shows a 22-23 km thick crust with velocities of be given elsewhere (e.g. Uenzelmann-Neben et al., this 2.0-3.5 km/s for the sediments above the acoustic volume).
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